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U D D U Fe Zn Fe R R Zn Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe Fe G Fe Fe Fe R Fe Fe Fe Fe Fe 17 49 21 53 45 21 85 42 72 68 50 52 58 27 53 63 15 39 55 43 56 27 77 51 20 43 65 70 70 77 79 57 87 37 65 29 30 60 50 79 40 50 78 25 50 26 86 35 47 76 22 48 47 87 40 42 53 73 32 45 63 40 81 37 42 70 22 33 72 42 34 67 43 40 17 56 70 85 43 26 88 50 46 51 60 67 45 38 25 85 66 54 55 45 50 50 44 34 62 29 22 53 42 11 62 14 63 28 26 62 35 17 48 21 44 45 32 65 52 Ybs Ygp Yps Ygp Yps _l Yps Ym Ypa Ygp Yps Yps Yp Ylo Ym Ymp Ylb Yps SOl Ybs Zd Ygp Ylo Ygp Yps Zd Yfw Ymp Yp Yb Ylo Ylb _h Ylh Ylb Ymh Zd Yp Yh Yk Ybh Sl Ym Ylo Dcw Ygp Yp Yps _a Ypg Ypa Ym Ypg Ylh Ylb Ylo Ybh Zch Ylh Ybh Ym Ylo Ybh Ybh Ybs Yb Ypg Yps Yp Yp Yp Yma Ym Dcw Ylh _h Sbp Yb _a Sg Yb Ya Yh Zd Ybh Ylb Ybh Ypa Zd Ype Yp Ybh Ypa _h Ya Ybs _a Zd Zd Ypg Ygp Ygp Ylb Ygp Yp Ygp Ya Ygp Ygp Yps Ylh Yps Ybh Ygp Yp Ylo Ylb Yp Yps Zd Ym Yps Yp Yk Yb Ylb Ype Yh Yp _l Yk Ylh Ybs Ylo Ylh Yk Ylb Ymp Sbp Ybh Yp Dkec Zch Ya Dbv Ybs Ym Ylb Ym Yk Ylb Ya Yp Ybh Zch Ylb Ybs Yb Yff Ypg Ylo Ylo Ylo Sg Ymh Yk Ybh Ylo Ylo Ylo Dkec Ypa _l Sl Ylh Ylb Yb Ylo Yp Zd Ym Ypg Zd Yb Ybs Ya Ybs Ybs Ylo Zd Ypg _l Ybh Ypg Ya Zd Yp Ylo Ylo Yff _a Ybh Ybs Ybh Yh Yp Ybs Ylo Dcw Sg Dbv Yps Yp Yb Ypg Ypg Ypg Ypg Ym Ym Ylo Ylo Ylo 64 80 57 60 74 43 63 65 73 0 66 81 56 79 81 84 62 75 73 80 61 71 67 66 59 57 73 69 69 58 40 67 69 70 45 83 46 38 76 65 53 57 65 59 69 74 53 83 83 43 68 77 70 63 54 61 73 82 33 72 79 61 70 62 62 72 63 49 71 61 58 79 52 60 71 85 41 58 69 60 47 78 84 63 71 56 66 70 41 64 87 81 77 47 70 84 70 65 76 52 74 73 50 66 83 84 58 68 81 65 83 54 51 82 51 64 62 75 54 46 60 71 84 65 63 79 71 78 78 67 75 62 70 56 56 36 33 34 53 62 57 64 49 49 84 70 84 67 64 65 65 58 48 48 45 59 70 84 78 63 79 83 60 86 64 64 70 68 54 73 41 77 73 67 54 74 58 50 84 45 0 80 62 41 31 65 60 79 85 70 71 32 58 48 84 70 58 69 79 78 35 41 60 74 69 79 79 59 66 64 63 59 46 54 82 80 76 51 61 66 83 82 78 76 62 69 80 82 49 56 70 69 48 78 53 68 64 70 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79 52 84 69 46 66 73 35 62 74 77 57 66 66 40 68 71 44 86 57 44 54 55 38 69 84 54 62 79 69 59 84 82 65 83 62 43 48 79 81 75 84 78 49 70 79 70 65 64 83 60 79 71 77 52 65 61 69 81 75 82 71 51 60 75 55 67 80 69 72 71 42 58 83 54 74 64 61 62 67 77 74 74 56 37 50 35 57 64 52 54 78 50 61 56 78 80 67 75 53 71 63 53 67 73 69 71 74 73 63 76 56 74 81 65 47 71 74 69 44 64 80 71 69 49 60 53 58 73 66 65 59 40 78 46 65 78 65 86 84 47 59 73 48 83 60 54 50 52 57 47 58 59 77 69 83 79 81 80 66 73 59 24 68 83 58 54 67 54 80 86 39 82 58 76 62 67 65 75 59 76 69 84 45 57 75 46 41 49 76 74 79 72 81 61 65 79 0 46 77 59 39 70 70 57 62 55 73 58 79 76 76 39 56 61 69 73 46 78 66 65 70 60 49 70 74 36 64 61 47 76 69 55 63 42 67 63 76 87 79 72 74 53 67 61 46 83 67 56 83 56 65 71 75 79 49 72 63 77 68 66 30 Fe 67 16 33 29 14 20 31 19 24 45 76 25 38 19 44 53 22 35 37 26 36 42 18 35 27 13 35 83 47 26 73 34 31 80 31 Ypg Ym Yh 55 _a 36 _a _a Fe Fe Fe Fe Fe 85 78 Dkec Dkec Dcw Dcw Dcw Ylo Yh Yh Dcw Ylo Ylb Yb Ymp Ylo Yp Ylh Ylo Ylo Ylo Yh Sg Sg Sg 74 o 37’30’’ 41 o 07’30’’ (BRANCHVILLE) 41 o 07’30’’ 74 o 30’ (WAWAYANDA) 41 o 00’ 74 o 30’ (BOONTON) 41 o 00’ 74 o 37’30” (STANHOPE) 35’ 32’30” (DOVER) (HAMBURG) 5’ 5’ 35’ 32’30” (NEWTON EAST) (NEWFOUNDLAND) 2’30’’ 2’30’’ A A’ B B’ 1,00 SEA -1,00 -2,00 F 2,00 1,000 SEA LEVEL -1,000 -2,000 FEET 2,000 B B’ Wallkill River Sparta Thrust Fault East Fault Reservoir Fault Russia Fault Bowling Green Mountain Longwood Valley Fault Longwood Valley Gorge Fault Ybh Ybh Yb Yb Ypg Ypg Ypg Ypg Ypg Ypg Yp Yp Yp Yp Ylo Ylo Ylo Ylo Ym Ym Yk Ybs Ybs _a _l _h Yu Yu Ymh Yps Ypg Yps Yps Yps Yps Yb Ylb Yba Dcw Dkec Dkec Dkec Dbv Dcw Sbp Sbp Sbp Sg Sg Sg Sl Sl Sl Ym Yps Ymh Ybh Ybh Ymh _h 1,000 SEA LEVEL -1,000 -2,000 FEET 2,000 A 1,000 SEA LEVEL -1,000 -2,000 FEET 2,000 A’ Hamburg Fault Tranquility Thrust Fault Zero Fault East Fault _l _a _a _l _h _h Ylo Ya Ylb Ym Ylo Ya Ylb _a _h _l Ylo Ym Ylb Ym Ylb Yfw Ylb Ylo Ylo Ygp Ygp Yp Yp Ygp Yu Ym Ylb Ygp Ylh Yff _a _a _h _l Yu Yff Ybh Ybs Ybh Ylo Ybs Yk Ylb Ypg Ype Ype Ymp Yh Ym Ylo Ylo Yb Yb Ylh Ylh Yp Ypg Ybh Yb Ylo CORRELATION OF MAP UNITS GREEN POND MOUNTAIN REGION Unconformity Unconformity Unconformity Unconformity NEW JERSEY HIGHLANDS Intrusive Contacts Vernon Supersuite Byram Intrusive Suite Lake Hopatcong Intrusive Suite Back Arc Supracrustal Rocks Intrusive Contacts Magmatic Arc Rocks Losee Metamorphic Suite Other Rocks KITTATINNY VALLEY SEQUENCE Intrusive Contacts Intrusive Contacts Kittatinny Supergroup VALLEY AND RIDGE Beemerville Intrusive Suite Dbv Dcw Dkec Sbp Sl Sg _a _l _h Ya Ylh Yma Yh Ylb Ylo Yk Ym Yb Ymh Ymp Yp Ype Yff/Yfw Ybh Ybs Ypg Ypa Yps Ygp Zch Zd SOl Yu DEVONIAN SILURIAN SILURIAN and ORDOVICIAN CAMBRIAN NEOPROTEROZOIC MESOPROTEROZOIC N % 5 10 15 20 5 10 15 20 Avg trend = N46 o E Sector angle = 10 o n = 67 Figure 1. Rose diagram of bedding strikes in Lower Paleozoic rocks of the Kittatinny Valley sequence. N % 10 5 15 20 10 15 20 Avg trend = N66 o W Sector angle = 10 o n = 28 Figure 3. Rose diagram of joint strikes in Lower Paleozoic rocks of the Kittatinny Valley sequence. N % 10 10 20 30 20 30 Avg trend = N59 o W Sector angle = 10 o n = 957 Figure 4. Rose diagram of joint strikes in Mesoproterozoic rocks. N % 10 20 10 20 Avg trend = N34 o E Sector angle = 10 o n = 943 Figure 2. Rose diagram of crystallization foliation strikes in Mesoproterozoic rocks. Bedrock geology mapped by R.A. Volkert and D.H Monteverde in 1987, 2005 and 2012. Middle Paleozoic geology adapted from S.G. Barnett III (1976) and G.C. Herman and J.P. Mitchell (1991). Digital cartography by R.S. Pristas and N.L. Malerba. Reviewed by E. Verbeek and M. Gorring. Research supported by the U. S. Geological Survey, National Cooperative Geologic Mapping Program, under USGS award number 05HQAG0026. The views and conclusions contained in this document are those of the author and should not be interpreted as necessarily representing the official policies, either expressed or implied, of the U. S. Government. Mapped by the Army Map Service. Edited and published by the United States Geological Survey, 1954 Control by USGS, USC&GS, and New Jersey Geodetic Survey Topography form aerial photographs by stereophotogrammetric meth- ods. Aerial photographs taken 1942. Culture revised by the United States Geological Survey 1954. Polyconic projection. 1927 North American datum 10,000-foot grid based on New Jersey coordinate system 1000-meter Universal Transverse Mercator grid ticks, zone 18. Bedrock Geologic Map of the Franklin Quadrangle Sussex and Morris Counties, New Jersey by Richard A. Volkert and Donald H. Monteverde 2013 LOCATION IN NEW JERSEY 7000 FEET 000 000 0 2000 3000 4000 5000 6000 .5 1 KILOMETE R 1 0 SCALE 1:24 000 2 1 0 1 MILE 1 , 1 .5 CONTOUR INTERVAL 20 FEET DEPARTMENT OF ENVIRONMENTAL PROTECTION WATER RESOURCES MANAGEMENT NEW JERSEY GEOLOGICAL AND WATER SURVEY Prepared in cooperation with the U.S. GEOLOGICAL SURVEY NATIONAL GEOLOGIC MAPPING PROGRAM BEDROCK GEOLOGIC MAP OF THE FRANKLIN QUADRANGLE SUSSEX AND MORRIS COUNTIES, NEW JERSEY GEOLOGIC MAP SERIES GMS 13-3 62 40 Fe 65 18 33 U D R R U D Contact - Dotted where concealed Fault - Dotted where concealed. Queried where uncertain. Arrow shows dip direction and attitude of fault, where known. Normal fault - U, upthrown side; D, downthrown side Reverse fault - U, upthrown side; D, downthrown side Strike slip - Arrows indicate relative horizontal movement Inclined thrust fault - teeth on upper plate Brittle deformation zone FOLDS Folds in Proterozoic rocks showing trace of axial surface, direction and dip of limbs, and direction of plunge. Overturned antiform Overturned synform Antiform Synform Folds in Paleozoic rocks showing trace of axial surface, direction and dip of limbs, and direction of plunge. Folds in bedding and/or cleavage. Anticline Syncline PLANAR FEATURES Strike and dip of beds Inclined Vertical Overturned Strike and dip of crystallization foliation Inclined Vertical Strike and dip of mylonitic foliation LINEAR FEATURES Bearing and plunge of mineral lineation in Proterozoic rocks OTHER FEATURES Abandoned mine - Fe, magnetite; Zn, zinc; G, graphite Abandoned rock quarry Active rock quarry Bedrock float used to construct map Form line showing foliation in Mesoroterozoic rocks. Shown in cross section only. EXPLANATION OF MAP SYMBOLS MAGNETIC NORTH APPROXIMATE MEAN DECLINATION, 2005 TRUE NORTH 13 ° INTRODUCTION The Franklin quadrangle is located in southeastern Sussex County, northwestern Mor- ris County, and western Passaic County, where it straddles the boundary between the New Jersey Highlands and Valley and Ridge physiographic provinces, but it is predominantly in the Highlands. The area is characterized by rugged uplands with ridge top elevations of as much as 1,410 ft. above sea level, separated by broad, generally northeast-striking stream valleys. The valleys are drained by the Wallkill River in the west, the Pequannock River in the northeast, and the Rockaway River in the southeast. Previous work on the bedrock geology of the quadrangle includes that of Spencer and others (1908), Hague and others (1956), Baker and Buddington (1970), and Drake and others (1996). The bedrock lithologies and structures depicted on these maps lacks confor- mity with more recent detailed mapping of adjacent areas. Moreover, new interpretations of bedrock geologic relationships, based in part on detailed bedrock mapping, major and trace element geochemistry, stable isotope analysis, and uranium-lead (U-Pb) geochronology, have updated much of the previous work. STRATIGRAPHY Paleozoic rocks Paleozoic rocks in the map area range in age from Cambrian through Devonian and are subdivided into the Middle Paleozoic rocks of the Green Pond Mountain Region and Lower Paleozoic rocks of the Kittatinny Valley sequence. Middle Paleozoic rocks crop out in the Green Pond Mountain Region, a northeast-trending block of downfaulted and folded sedi- mentary rock in the southeast part of the area. They include the Green Pond Conglomerate, Longwood Shale, Poxino Island, and Berkshire Valley Formations of Silurian age, and the Connelly Conglomerate, Esopus Formation, Kanouse Sandstone, Cornwall Shale, and Bell- vale Sandstone of Devonian age. The stratigraphic relationships of the Middle Paleozoic rocks were discussed by Darton (1894), Kümmel and Weller (1902), Barnett (1970), and Herman and Mitchell (1991). Formations of Cambrian through Ordovician age of the Kittatinny Valley sequence crop out in the lowland areas of the Wallkill Valley, Wildcat Brook, and Big Springs, where they unconformably overlie, or are in fault contact with, Mesoproterozoic rocks. The Kittatinny Valley sequence was previously considered part of the Lehigh Valley sequence of MacLachlan (1979) but was reassigned by Drake and others (1996). It includes the Kittatinny Supergroup, of which the Leithsville Formation and Allentown Dolomite are exposed in the quadrangle. Based on the final acceptance of the Global Stratotype Section and Point base (GSSP) for the Ordovician at Green Point, Newfoundland (Cooper and others, 2001), the Cambrian-Ordovician boundary in New Jersey is now accepted as occurring within the lower third of the Epler Formation, at the top of the Cordylodus lindstromi zone, within conodont fauna B as used in Karklins and Repetski (1989). Therefore, the Allentown Dolomite is now regarded as Cambrian in age. North of Franklin Pond, northwest-striking lamprophyre dikes of Lower Silurian to Upper Ordovician age of the Beemerville Intrusive Suite (Drake and Monteverde, 1992) intrude the Franklin Marble of Mesoproterozoic age, and the west limb of the zinc orebody at the Franklin mine. Elsewhere regionally, titanite from nepheline syenite at Beemerville yields a TIMS U-Pb crystallization age of 447 ± 2 Ma (Ratcliffe and others, 2012), a K-Ar cooling age from biotite of 435 ± 20 Ma (Zartman and others, 1967), and a fission-track age from titanite of 422 ± 14 Ma (Eby and others, 1992). Neoproterozoic rocks Mesoproterozoic rocks along the eastern side of the Wallkill Valley, north of Morris Lake, and along the southwestern part of Bowling Green Mountain, are unconformably overlain by unmetamorphosed rocks of the Neoproterozoic Chestnut Hill Formation (Drake, 1984; Gates and Volkert, 2004). Elsewhere regionally, the Chestnut Hill Formation is unconform- ably overlain by the Lower Cambrian Hardyston Quartzite. Rocks of the Chestnut Hill For- mation were formed from alluvial, fluvial, and lacustrine sediments, and possible volcanic rocks of felsic composition, that were deposited in a series of small sub-basins along the rifted margin of eastern Laurentia at about 600 Ma during breakup of the supercontinent Rodinia (Volkert and others, 2010a). Mesoproterozoic rocks in the map area, but not the Cambrian or younger Paleozoic rocks, are intruded by east or northeast-striking diabase dikes of Neoproterozoic age (Volk- ert and Puffer, 1995). The dikes are characterized by sharp, mainly discordant contacts against enclosing country rocks, aphanitic chill margins, and they contain xenoliths of Me- soproterozoic rocks. Some dikes have columnar joints along their margins, suggesting that the magma may locally have broken the surface as flows that are now eroded. Dikes have geochemical compositions that are high in TiO 2 , P 2 O 5 , Zr, and light rare-earth elements, indicating they were formed from an Ocean Island Basalt-like mantle source in a rift-relat- ed, within-plate, tectonic setting (Volkert, 2004a). Contacts between diabase dikes and the Chestnut Hill Formation are not known to be exposed in the Highlands, so the temporal relationship between them remains unknown. Mesoproterozoic rocks Mesoproterozoic rocks in the map area consist of an assemblage of granites, gneisses, and marble. Most Mesoproterozoic rocks were metamorphosed to granulite facies during the Ottawan phase of the Grenville orogenic cycle at 1045 to 1024 Ma (Volkert and others, 2010b). The temperature for this high-grade metamorphism is constrained from regional calcite-graphite geothermometry to 769 o C (Peck and others, 2006). Among the oldest Mesoproterozoic rocks in the area are the Losee Suite that formed in a magmatic arc, and a thick assemblage of supracrustal metavolcanic and metasedi- mentary rocks formed in a back-arc basin inboard of the Losee arc (Volkert, 2004b). Rocks of the Losee Suite are calc-alkaline in composition and include various quartz-plagioclase gneisses and amphibolite formed from plutonic and volcanic protoliths (Volkert and Drake, 1999). Rocks of the Losee Suite yield sensitive high-resolution ion microprobe (SHRIMP) U-Pb zircon ages of 1282 to 1248 Ma (Volkert and others, 2010b). Spatially and temporally associated with the Losee Suite are supracrustal rocks that include microcline gneiss and amphibolite formed from felsic and mafic volcanic protoliths, respectively, and quartzofeldspathic gneisses, calc-silicate rocks, and marble formed from sedimentary protoliths. Microcline gneiss yields U-Pb SHRIMP zircon ages of 1299 to 1251 Ma (Volkert and others, 2010b) that closely overlap the age of rocks of the Losee Suite. Granite and related rocks of the Byram and Lake Hopatcong Intrusive Suites, that to- gether comprise the Vernon Supersuite (Volkert and Drake, 1998), are abundantly exposed in the map area where they intrude Losee Suite and supracrustal rocks. Byram and Lake Hopatcong rocks form a complete differentiation series that includes monzonite, quartz monzonite, granite, and alaskite, all of which have a distinctive A-type geochemical compo- sition (Volkert and others, 2000). Granite of both suites yields similar U-Pb SHRIMP zircon ages of 1188 to 1182 Ma (Volkert and others, 2010b). The youngest Mesoproterozoic rocks are postorogenic potassic granites and granite pegmatites that are undeformed, contain xenoliths of foliated gneiss or marble, and intrude other Mesoproterozoic rocks in the map area as small, tabular to irregular bodies that are discordant to the metamorphic foliation. Pegmatite known locally as Double Rock, that in- trudes marble and the west limb of the zinc orebody at the Franklin mine, has a U-Pb zircon age of 986 Ma, and other regional postorogenic bodies of granite and pegmatite yield U-Pb zircon ages of 1004 to 990 Ma (Volkert and others, 2005). STRUCTURE Paleozoic bedding and cleavage Bedding in the Paleozoic rocks is fairly uniform and strikes northeast except in the hinge areas of folds at Bowling Green Mountain. The average strike of bedding in Middle Paleozoic rocks of the Green Pond Mountain Region is N.39 o E. Beds range in dip from 22 o to 90 o and average 60 o . Most beds are upright and dip northwest and, less commonly, southeast, although locally in the Longwood Valley they are overturned. The average strike of bedding in Lower Paleozoic rocks of the Kittatinny Valley sequence is N.46 o E. (fig. 1). Beds range in dip from 11 o to 90 o and average 44 o . They dip mainly northwest and, less commonly, southeast. Cleavage (closely spaced parallel partings) is present in most of the Paleozoic rocks but is best developed in shale and other fine-grained rocks. Cleavage in rocks of the Green Pond Mountain Region strikes about N.43 o E. and in rocks of the Kittatinny Valley sequence about N.53 o E., nearly parallel to the strike of bedding in both the Middle and Lower Pa- leozoic rocks. Cleavage dips mainly southeast at an average of 75 o in Middle Paleozoic rocks, and toward the northwest or southeast at an average of 43 o in the Lower Paleozoic rocks. Proterozoic foliation Crystallization foliation, formed by the parallel alignment of mineral grains in the Me- soproterozoic rocks, defines the trend of the bedrock. It is an inherited feature from com- pressional stresses during granulite-facies metamorphism that deformed the rocks between 1045 and 1024 Ma (Volkert and others, 2010b). Foliation strikes mainly northeast at an average of N.34 o E. (fig. 2), but locally, in the hinges of folds, it strikes northwest because of deformation of the rocks during folding. Foliation dips southeast and, less commonly, north- west at 30 o to 90 o and averages 65 o . Northwest-striking foliation dips gently to moderately northeast. Folds Folds in the Paleozoic rocks were formed during the Taconian and Alleghanian oroge- nies at about 450 Ma and 250 Ma, respectively. Folds in the Green Pond Mountain Region are northeast, open to tight, upright to locally overturned, and gently inclined to recumbent anticlines and synclines (Barnett, 1976; Herman and Mitchell, 1991). Most folds plunge gently southwest. Taconic-age folds here are cut by younger Alleghanian faults (Herman and Monteverde, 1989; Herman and others, 1997). Folds in rocks of the Kittatinny Valley sequence are northeast, open, upright, and form gently north-plunging anticlines and syn- clines that continue from Lake Mohawk to the south (Drake and Volkert, 1993). Folds that deform Mesoproterozoic rocks originated during the Ottawan phase of the Grenville orogeny. They deform earlier-formed planar metamorphic fabrics and, therefore, postdate the development of crystallization foliation. Characteristic fold patterns are broad, open, northwest-verging to locally upright, northeast-plunging antiforms and synforms. Min- eral lineations plunge parallel to the axes of major folds. Plunges range from 13 o to 53 o and average 31 o N.52 o E. Faults The structural geology of the bedrock units is dominated by northeast-trending faults that deform Mesoproterozoic and Paleozoic rocks. Most faults are characterized by brit- tle deformation features that include brecciation, recrystallization and low-temperature retrogression of mafic minerals, chlorite or epidote-coated slickensides, and close-spaced fracture cleavage. The Zero and Reservoir faults are characterized by ductile deformation features that include mylonite, shear band foliation, and boudinage, overprinted by brittle deformation features. The Tranquility thrust fault strikes northeast and dips gently to moderately southeast at an average of 35 o . The fault places Mesoproterozoic and Paleozoic rocks on the hanging wall against Paleozoic dolomite on the footwall. It extends through the northwest corner of the map area, and is also known to the southwest, in the Tranquility quadrangle, where it was encountered in drill core by New Jersey Zinc Company geologists (Baum, 1967), and in the Newton East quadrangle, where the fault was inferred by Drake and Volkert (1993), and later confirmed through drilling in 2009 at the Limecrest quarry (Volkert, 2010). The fault is characterized by early ductile deformation that is strongly overprinted by brittle deformation features. The Hamburg fault strikes northeast and dips southeast at about 75 o . It places Meso- proterozoic rocks on the footwall against Paleozoic rocks on the hanging wall along most of its length. The latest movement appears to have been normal. The fault is characterized by brittle deformation features along its entire length. The Zero fault strikes northeast and dips steeply southeast to vertically. It bounds the west side of the Wallkill River Valley where it places Mesoproterozoic rocks on the footwall against Paleozoic rocks on the hanging wall. The fault is characterized by ductile deforma- tion features of Proterozoic age that are overprinted by brittle deformation fabric of probable Paleozoic age (Metsger, 2001). The fault has a protracted history of movement through geologic time, but the latest movement sense appears to be normal. The Zero fault termi- nates in a series of splays in the northern part of the map area where it is cut off by the East fault. The Sparta thrust fault strikes northeast and dips nearly horizontally to about 35 o south- east. To the south, in the Newton East quadrangle, it was interpreted as a northwest-dipping back thrust (Drake and Volkert, 1993), but it is here reinterpreted as a folded thrust fault based on movement indicators in Allentown Dolomite near Sparta. The fault is cut off on both ends by the Zero fault. The Sparta thrust fault has Paleozoic rocks along most of its length, but in the map area it extends along the east side of the Wallkill River Valley, where it has Paleozoic rocks on the footwall and Mesoproterozoic rocks on the hanging wall. The fault is characterized by brittle deformation fabric along its entire length. The East fault strikes northeast and dips southeast about 80 o . It borders the east side of the Wallkill River Valley, where it has Mesoproterozoic rocks along most of its length, but in the map area it places Paleozoic rocks on the footwall against Mesoproterozoic rocks on the hanging wall. The latest movement on the fault appears to have been reverse. The fault is characterized by brittle deformation fabric along its entire length. The Reservoir fault strikes northeast and ranges in dip from steeply northwest to steeply southeast. It places Mesoproterozoic rocks on the footwall against Paleozoic rocks on the hanging wall along most of its length. The fault has undergone multiple reactivations dating from the Proterozoic that indicate normal, right-lateral strike slip, and reverse movement, with latest movement having been normal. The fault is characterized by ductile deformation features in the center of the fault zone that are overprinted by a zone of brittle deformation as much as 1,000 feet wide. The Russia fault (Herman and Mitchell, 1991) strikes N.50 o E., closely paralleling the adjacent Reservoir fault, and dips southeast at about 80 o . It is bounded by Paleozoic rocks on both sides. South of the map area the fate of the fault is unknown, and to the north, in the Newfoundland quadrangle, it merges with, or is cut off by, the Reservoir fault. Latest movement on the fault appears to have been normal. The fault is characterized by brittle deformation fabric. The Longwood Valley fault strikes about N.45 o E. and dips steeply northwest to verti- cally. It has Mesoproterozoic rocks on the footwall and Paleozoic rocks on the hanging wall along most of its length. Kinematic indicators suggest the latest movement on the fault was reverse, although dip-slip normal movement is predominant south of the map area. The fault is characterized by brittle deformation fabric. Mesoproterozoic and Paleozoic rocks are also deformed by small faults striking north- east or northwest that range from a few inches to tens of feet wide and are rarely more than a few thousand feet long. These faults are characterized mainly by brittle deformation features. Latest movement is varied and ranges from normal, to right-lateral or left-lateral strike slip. Joints Joints are a ubiquitous feature in the Mesoproterozoic and Paleozoic rocks but are best developed in massive rocks such as Paleozoic limestone, dolomite, and sandstone, and in Mesoproterozoic granite and some gneiss. Joints developed in Mesoproterozoic rocks are characteristically planar, moderately well formed, moderately to widely spaced, and moder- ately to steeply dipping. Their surfaces are typically unmineralized, except near faults, and are smooth and less commonly slightly irregular. Joints are varied in their spacing from a foot to tens of feet apart. Those formed close to faults are spaced 2 feet or less apart. The dominant joints in the Green Pond Mountain Region strike N.49 o W. on average and dip mainly northeast at an average of 76 o . Joints in rocks of the Kittatinny Valley sequence strike N.66 o W. on average (fig. 3) and dip southwest at an average of 76 o . A minor set strikes N.35 o E. and dips nearly equally southeast or northwest at an average of 53 o . The dominant joints in the Mesoproterozoic rocks are nearly perpendicular to the strike of crystallization foliation, a consistent feature in Mesoproterozoic rocks throughout the Highlands (Volkert, 1996). Therefore, the strike of joints is somewhat varied because of folding. The dominant joints strike N.59 o W. (fig. 4) and dip moderately to steeply southwest at an average of 76 o . ECONOMIC RESOURCES Mesoproterozoic rocks in the quadrangle host economic deposits of iron ore (magne- tite), zinc ore (franklinite, zincite, and willemite), and graphite that were mined predominant- ly during the 19th century. Magnetite was extracted from mines hosted by Mesoproterozoic granite, gneiss, and, very locally, marble. Detailed descriptions of most of the mines are given in Bayley (1910) and Baker and Buddington (1970). Marble-hosted zinc-iron-manga- nese ore was mined at the world-famous Franklin mine (Frondel and Baum 1974) and Ster- ling Hill mine (Metsger and others, 1958, Metsger, 2001, Johnson, 2001) in the northwest part of the map area. Both zinc deposits have been the subject of geologic inquiry for more than a century, and a complete bibliography of references pertaining to these deposits is given in Dunn (1995). Graphite was mined during the 19th century from rusty-weathering biotite-quartz-feldspar gneiss at a single location west of Oak Ridge Reservoir. Mesoproterozoic marble in the northwest part of the map was quarried for crushed stone at several locations, and is currently quarried at a single location north of the Sterling Hill mine. The Neoproterozoic Chestnut Hill Formation hosts a deposit of hematite that was mined during the 19th century on the east side of the Wallkill River Valley. The deposit was small, and no record of mining is known, so this may not have been a producing mine. DESCRIPTION OF MAP UNITS Green Pond Mountain Region Bellvale Sandstone (Middle Devonian) (Bellvale Flags of Darton, 1894; Willard, 1937) - Upper beds are grayish-red to grayish-purple sandstone containing quartz pebbles as large as 1 in. in diameter. Lower beds are light-olive-gray to yellowish-gray- and green- ish-black-weathering, medium-gray to medium-bluish-gray, very thin to very thick-bed- ded siltstone and sandstone, crossbedded, graded, and interbedded with black to dark- gray shale. More sandstone occurs in upper beds and is finer downward. Lower contact conformable with the Cornwall Shale and placed where beds are thicker and volume of shale and siltstone is about equal. Unit is 1,750 to 2,000 ft. thick. Cornwall Shale (Middle Devonian) (Hartnagel, 1907) – Black to dark-gray, very thin to thick-bedded, fossiliferous shale, interbedded with medium-gray and light-olive-gray to yellowish-gray, laminated to very thin bedded siltstone that is more abundant in upper part. Lower contact with Kanouse Sandstone probably conformable. Unit is about 950 ft. thick. Kanouse Sandstone, Esopus Formation, and Connelly Conglomerate, undivided (Lower Devonian) Kanouse Sandstone (Kümmel, 1908) – Medium-gray, light-brown, and grayish-red, fine to coarse-grained, thin to thick-bedded sandstone and pebble con- glomerate. Basal conglomerate is interbedded with siltstone and contains well-sorted, subangular to subrounded, gray and white quartz pebbles less than 0.4 in. long. Lower contact with Esopus Formation gradational. Unit is about 46 ft. thick. Esopus Formation (Vanuxem, 1842; Boucot, 1959) – Light to dark-gray, laminated to thin-bedded siltstone interbedded with dark-gray to black mudstone, dusky-blue sand- stone and siltstone, and yellowish-gray, fossiliferous siltstone and sandstone. Lower contact probably conformable with Connelly Conglomerate. Unit is about 180 ft. thick in the map area. Connelly Conglomerate (Chadwick, 1908) – Grayish-orange-weathering, very light-gray to yellowish-gray, thin-bedded quartz-pebble conglomerate. Quartz pebbles are subround- ed to well rounded, well sorted, and as much as 0.8 in. long. Unit is about 36 ft. thick. Berkshire Valley and Poxono Island Formations, undivided (Upper Silurian) Berkshire Valley Formation (Barnett, 1970) – Yellowish-gray-weathering, medium-gray to pink- ish-gray, very thin to thin-bedded fossiliferous limestone interbedded with gray to green- ish-gray calcareous siltstone and silty dolomite, medium-gray to light-gray dolomite conglomerate, and grayish-black thinly laminated shale. Lower contact conformable with Poxino Island Formation. Unit ranges in thickness from 90 to 125 ft. Poxono Island Formation (White, 1882; Barnett, 1970) – Very thin to medium-bedded se- quence of medium-gray, greenish-gray, or yellowish-gray, mud-cracked dolomite; light- green, pitted, medium-grained calcareous sandstone, siltstone, and edgewise conglom- erate containing gray dolomite; and quartz-pebble conglomerate containing angular to subangular pebbles as much as 0.8 in. long. Interbedded grayish-green shale at lower contact is transitional into underlying Longwood Shale. Unit ranges in thickness from 160 to 275 ft. Longwood Shale (Upper to Middle Silurian) (Darton, 1894) – Dark reddish-brown, thin to very thick-bedded shale interbedded with cross-bedded, very dark-red, very thin- to thin-bedded sandstone and siltstone. Lower contact conformable with Green Pond Conglomerate. Unit is about 330 ft. thick. Green Pond Conglomerate (Middle to Lower Silurian) (Rogers, 1836) - Medium to coarse- grained quartz-pebble conglomerate, quartzitic arkose and orthoquartzite, and thin to thick-bedded reddish-brown siltstone. Grades downward into less abundant gray, very dark red, or grayish-purple, medium to coarse-grained, thin- to very thick-bedded peb- ble to cobble-conglomerate containing clasts of red shale, siltstone, sandstone, and chert; yellowish-gray sandstone and chert; dark-gray shale and chert; and white-gray and pink milky quartz. Quartz cobbles are as much as 4 in. long. Unconformably over- lies, or is in fault contact with, Mesoproterozoic rocks. Unit is about 1,000 ft. thick. Valley and Ridge Beemerville Intrusive Suite Lamprophyre dikes (Lower Silurian to Upper Ordovician) – Light-medium- to medi- um-dark-gray, fine-grained to aphanitic dike of mainly alkalic composition. Contacts are chilled and sharp against enclosing Mesoproterozoic country rock. Dike is exposed in the Buckwheat open cut at the Franklin zinc mine, north of Franklin Pond. It is as much as 25 ft. wide and of uncertain length. Kittatinny Valley Sequence Allentown Dolomite (Upper Cambrian) (Wherry, 1909) – Upper sequence is light-gray- to medium-gray-weathering, medium-light- to medium-dark-gray, fine to medium-grained, locally coarse-grained, medium to very thick-bedded dolomite; local shaly dolomite near the bottom. Floating quartz sand and two series of medium-light- to very light-gray, medium-grained, thin-bedded quartzite and discontinuous dark-gray chert lenses occur directly below upper contact. Lower sequence is medium- to very-light-gray-weathering, light- to medium dark-gray, fine to medium-grained, thin to medium-bedded dolomite and shaly dolomite. Weathered exposures characterized by alternating light and dark- gray beds. Ripple marks, ooids, algal stromatolites, cross-beds, edgewise conglomer- ate, mud cracks, and paleosol zones occur throughout but are more abundant in lower sequence. Lower contact gradational into Leithsville Formation. Unit contains a trilobite fauna of Dresbachian (early Late Cambrian) age (Weller, 1903; Howell, 1945). Unit is about 1,800 ft. thick regionally. Leithsville Formation (Middle to Lower Cambrian) (Wherry, 1909) – Upper sequence, rarely exposed, is mottled, medium-light- to medium-dark-gray-weathering, medium- to medium-dark-gray, fine to medium-grained, medium to thick-bedded, locally pitted and friable dolomite. Middle sequence is grayish-orange or light- to dark-gray, gray- ish-red, light-greenish-gray- or dark-greenish-gray-weathering, fine-grained, thin to medium-bedded dolomite, argillaceous dolomite, dolomitic shale, quartz sandstone, siltstone, and shale. Lower sequence is medium-light- to medium-gray-weathering, medium-gray, fine to medium-grained, thin- to medium-bedded dolomite. Quartz-sand lenses occur near lower gradational contact with Hardyston Quartzite. Archaeocyathids of Early Cambrian age are present in formation at Franklin, New Jersey, suggesting an intraformational disconformity between Middle and Early Cambrian time (Palmer and Rozanov, 1967). Unit also contains Hyolithellus micans (Offield, 1967; Markewicz, 1968). Thickness is approximately 800 ft. regionally. Hardyston Quartzite (Lower Cambrian) (Wolff and Brooks, 1898) – Medium to light-gray, fine to coarse-grained, medium to thick-bedded pebble conglomerate, quartzite, arkosic sandstone and dolomitic sandstone. Conglomerate contains subangular to subrounded white quartz pebbles as much as 1 in. long. Lower contact unconformable with Meso- proterozoic rocks. Contains Scolithus linearis (?) and fragments of the trilobite Olenellus thompsoni of Early Cambrian age (Nason, 1891; Weller, 1903). Thickness regionally is as much as 30 ft. New Jersey Highlands Diabase dikes (Neoproterozoic) (Volkert and Puffer, 1995) – Light-gray or brown- ish-gray-weathering, dark-greenish-gray, aphanitic to fine-grained dikes. Composed principally of plagioclase (labradorite to andesine), augite, and iron-titanium oxides. Py- rite blebs are common. Contacts are chilled and sharp against enclosing Mesoprotero- zoic rocks. Dikes are as much as 40 feet wide and 0.5 mile or more long. Chestnut Hill Formation (Neoproterozoic) (Drake, 1984; Gates and Volkert, 2004) – In- terbedded sequence of gray, brownish-gray, greenish-gray, tan, or light green, medi- um-grained, thin-bedded lithic sandstone, quartzose sandstone, siltstone, pebble con- glomerate, and thin ironstone beds. Conglomerate contains subangular to subrounded clasts of quartz and feldspar. Interbedded coarser-grained lithologies locally are as much as 6 ft. thick, but are not laterally continuous and likely are channel deposits. Graded beds, tabular cross beds, rip-up clasts, slump folds, load casts, and clastic dikes are common. Thickness regionally is as much as 40 ft. Granite pegmatite (Mesoproterozoic) – Pinkish-gray or buff-weathering, pinkish-white or light-pinkish-gray, coarse- to very-coarse-grained, massive, unfoliated granite. Com- posed of microcline microperthite, quartz, oligoclase, and local hornblende. Intrudes most other Mesoproterozoic rocks in the map area as tabular to irregular bodies of varied thickness that are discordant to crystallization foliation. Vernon Supersuite (Volkert and Drake, 1998) Byram Intrusive Suite (Drake and others, 1991) Hornblende granite (Mesoproterozoic) – Pinkish-gray or buff-weathering, pinkish-white or light-pinkish-gray, medium- to coarse-grained, massive, foliated granite composed principally of microcline microperthite, quartz, oligoclase, hornblende, and local zircon, apatite, and magnetite. Unit grades into alaskite with decrease in concentration of horn- blende and into monzonite with decrease in quartz. Includes bodies of pegmatite and amphibolite too small to show on the map. Hornblende monzonite (Mesoproterozoic) – Pinkish-gray or buff-weathering, pinkish-gray or greenish-gray, medium to coarse-grained, massive, foliated monzonite, and less abundant syenite or quartz monzonite, composed of microcline microperthite, oligo- clase, hornblende, and quartz. Contains sparse amounts of pyroxene where in contact with rocks of the Lake Hopatcong Intrusive Suite. Lake Hopatcong Intrusive Suite (Drake and Volkert, 1991) Pyroxene granite (Mesoproterozoic) – Buff or white-weathering, greenish-gray, medium to coarse-grained, massive, foliated granite composed of mesoperthite to microantiper- thite, quartz, oligoclase, and clinopyroxene. Locally contains titanite, magnetite, apatite, and trace amounts of zircon and pyrite. Unit grades into alaskite with decrease in con- centration of clinopyroxene and into monzonite with decrease in quartz. Pyroxene alaskite (Mesoproterozoic) – Buff or white-weathering, greenish-buff or light- pinkish-gray, medium to coarse-grained, massive, moderately foliated granite com- posed of mesoperthite to microantiperthite, quartz, oligoclase, and sparse amounts of clinopyroxene. Commonly contains titanite, magnetite, apatite, and trace amounts of zircon. Pyroxene monzonite (Mesoproterozoic) – Gray, buff, or tan-weathering, greenish-gray, medium to coarse-grained, massive, moderately foliated monzonite to syenite. Com- posed of mesoperthite, microantiperthite to microcline microperthite, oligoclase, clino- pyroxene, titanite, magnetite, and sparse amounts of apatite and quartz. Back-Arc Basin Supracrustal Rocks Potassic feldspar gneiss (Mesoproterozoic) – Light-gray or pinkish-buff-weathering, pink- ish-white or light-pinkish-gray, medium-grained, moderately foliated gneiss composed of quartz, microcline microperthite, oligoclase, biotite, and magnetite. Garnet, tourma- line, and sillimanite occur locally. Microcline gneiss (Mesoproterozoic) – Pale pinkish-white-weathering, tan or pinkish-white, medium-grained, layered and foliated gneiss composed of quartz, microcline microper- thite, oligoclase, and biotite. Commonly contains garnet, magnetite, and trace amounts of sillimanite and tourmaline. Unit is spatially associated with marble or amphibolite. Biotite-quartz-feldspar gneiss (Mesoproterozoic) – Gray-weathering, locally rusty, gray, tan, or greenish-gray, medium to coarse-grained, moderately layered and foliated gneiss containing microcline microperthite, oligoclase, quartz, and biotite. Locally con- tains garnet, sillimanite, and magnetite; graphite and pyrrhotite are confined to the vari- ant that weathers rusty. Unit is spatially associated with amphibolite or pyroxene gneiss. Hornblende-quartz-feldspar gneiss (Mesoproterozoic) – Light-gray or pinkish-buff-weath- ering, pinkish-white or pinkish-gray, medium-grained, foliated gneiss composed of quartz, microcline microperthite, oligoclase, and hornblende. Locally contains biotite, garnet, and magnetite. Clinopyroxene-quartz-feldspar gneiss (Mesoproterozoic) – Pinkish-gray or pinkish-buff- weathering, white, pale-pinkish-white, or light-gray, medium to coarse-grained, mod- erately foliated gneiss composed of quartz, microcline, oligoclase, clinopyroxene, and trace amounts of epidote, biotite, titanite, and magnetite. Pyroxene gneiss (Mesoproterozoic) – White or tan-weathering, greenish-gray, medi- um-grained, layered and foliated gneiss composed of oligoclase, clinopyroxene, and titanite. Contains varied amounts of quartz, magnetite, scapolite, or calcite. Commonly interlayered with amphibolite or marble. Elsewhere, unit contains clots and layers of dark green, medium to coarse-grained rock mapped as diopsidite composed almost entirely of diopside to hedenbergite. Pyroxene-epidote gneiss (Mesoproterozoic) – Light-greenish-gray or greenish-pink- weathering, pale-pinkish-white or light-greenish-gray, medium-grained, layered and foli- ated gneiss containing quartz, oligoclase, pyroxene, epidote, microcline, scapolite, and titanite. Locally grades into pyroxene gneiss with decrease in epidote and microcline. Franklin Marble (Mesoproterozoic) – White, pink, or light-gray-weathering, white, light gray, orange, or pink, medium to coarse-grained, calcitic to locally dolomitic marble com- posed mainly of calcite, graphite, and phlogopite. Contains varied amounts of amphi- bole, clinopyroxene and other minerals. Separated by Hague and others (1956) into a lower Franklin marble layer (Yff) and an upper Wildcat marble layer (Yfw) that are separated by gneiss. Locally contains relict karst features that include bedrock pinna- cles, solution caves, and paleo-solution breccia. Franklin marble layer is host rock for zinc-iron-manganese deposits at the Franklin and Sterling Hill mines. Magmatic Arc Rocks Losee Metamorphic Suite (Drake, 1984; Volkert and Drake, 1999) Quartz-oligoclase gneiss (Mesoproterozoic) – White-weathering, light-greenish-gray, me- dium to coarse-grained, layered to massive, foliated gneiss composed of oligoclase or andesine, quartz, and varied amounts of hornblende, biotite, clinopyroxene, and mag- netite. Locally contains layers of amphibolite too thin to be shown on the map. Unit commonly has gradational contacts with biotite-quartz-oligoclase gneiss and hyperst- hene-quartz-plagioclase gneiss. Biotite-quartz-oligoclase gneiss (Mesoproterozoic) – Light-gray-weathering, gray or greenish-gray, medium to coarse-grained, layered and foliated gneiss composed of oligoclase or andesine, quartz, biotite, and trace amounts of garnet. Some outcrops contain hornblende. Unit locally contains thin, conformable layers of amphibolite. Hornblende-quartz-oligoclase gneiss (Mesoproterozoic) – White or light-gray-weather- ing, greenish-gray, medium to coarse-grained, foliated gneiss composed of oligoclase or andesine, quartz, hornblende, magnetite, and local clinopyroxene. Hypersthene-quartz-plagioclase gneiss (Mesoproterozoic) – Gray or tan-weathering, greenish-gray or greenish-brown, medium-grained, foliated gneiss composed of andes- ine or oligoclase, quartz, clinopyroxene, hornblende, and hypersthene. Commonly con- tains thin, conformable layers of amphibolite and quartz-plagioclase gneiss containing hornblende and clinopyroxene. Other rocks Amphibolite (Mesoproterozoic) – Grayish-black-weathering, black or grayish-black, me- dium-grained, foliated rock composed of hornblende, andesine, and magnetite. Some variants contain biotite and others contain clinopyroxene. Amphibolite associated with the Losee Suite is metavolcanic in origin, and that associated with supracrustal rocks may be metavolcanic or metasedimentary in origin. All types are shown undifferentiated on the map. Microantiperthite alaskite (Mesoproterozoic) – Tan or buff-weathering, light-greenish- gray, medium to coarse-grained, massive, indistinctly foliated rock composed of micro- antiperthite, brown rust-stained quartz, and oligoclase. Locally contains biotite, horn- blende, altered clinopyroxene, hypersthene, and magnetite. Confined to one small body south of Edison Pond. Mesoproterozoic rocks, undifferentiated – Shown in cross section only. Sbp Sl Sg SOl _a Ybh Ybs Ypg Ypa Yps Yk Ym Yb Ymh Ymp Yp Ype Yff/Yfw Ylo Ylb Ylh Yh Ya Yma Yu _l _h Zd Zch Ygp Dbv Dcw Dkec REFERENCES CITED AND USED IN CONSTRUCTION OF MAP Baker, D.R., and Buddington, A.F., 1970, Geology and magnetite deposits of the Franklin quadrangle and part of the Hamburg quadrangle, New Jersey: U.S. Geological Survey Professional Paper 638, 73 p. Barnett, S.G., III, 1970, Upper Cayugan and Helderbergian stratigraphy of southeastern New York and northern New Jersey: Geological Society of America Bulletin, v. 81, p. 2375-2402. ________, 1976, Geology of the Paleozoic rocks of the Green Pond outlier: New Jersey Geological Survey Geologic Report Series No. 11, 9 p. Baum, J.L., 1967, The Tranquility prospect, Sussex County, New Jersey: New Jersey Zinc Company, unpublished interoffice correspondence. On file in the office of the New Jersey Geological Survey, Trenton, New Jersey. 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Volkert, R.A., 2004a, Geochemistry and tectonic setting of late Neoproterozoic diabase dikes, New Jersey Highlands and Trenton Prong, in Puffer, J.H., and Volkert, R.A., eds., Field Guide and Proceedings of the 21st Annual Meeting of the Geological Association of New Jersey, p. 27-51. ________, 2004b, Mesoproterozoic rocks of the New Jersey Highlands, north-central Ap- palachians: petrogenesis and tectonic history: in Tollo, R.P., Corriveau, L., McLel- land, J., and Bartholomew, J., eds., Proterozoic tectonic evolution of the Grenville orogen in North America: Geological Society of America Memoir 197, p. 697-728. ________, 2010, Deep drilling at Limecrest quarry, Sparta, New Jersey: The Picking Table, v. 51, no. 1, p. 10-13. Volkert, R.A., Aleinikoff, J.N., and Fanning, C.M., 2010b, Tectonic, magmatic, and metamorphic history of the New Jersey Highlands: New insights from SHRIMP U-Pb geochronology, in Tollo, R.P., Bartholomew, M.J., Hibbard, J.P., and Karabi- nos, P.M., eds., From Rodinia to Pangea: The Lithotectonic Record of the Appala- chian Region, Geological Society of America Memoir 206, p. 307-346. Volkert, R.A., and Drake, A.A., Jr., 1998, The Vernon Supersuite: Mesoproterozoic A-type granitoid rocks in the New Jersey Highlands: Northeastern Geology and Environ- mental Sciences, v. 20, p. 39-43. ________, 1999, Geochemistry and stratigraphic relations of Middle Proterozoic rocks of the New Jersey Highlands, in Drake, A.A., Jr., ed., Geologic Studies in New Jersey and eastern Pennsylvania: U.S. Geological Survey Professional Paper 1565C, 77 p. Volkert, R.A., Feigenson, M.D., Patino, L.C., Delaney, J.S., and Drake, A.A., Jr., 2000, Sr and Nd isotopic compositions, age and petrogenesis of A-type granitoids of the Vernon Supersuite, New Jersey Highlands, USA: Lithos, v. 50, p. 325-347. Volkert, R.A., Monteverde, D.H., Gates, A.E., Friehauf, K.C., Dalton, R.F., and Smith, R.C., II, 2010a, Geochemistry and origin of Neoproterozoic ironstone deposits in the New Jersey Highlands and implications for the Iapetan rifted margin in the north-cen- tral Appalachians, in Tollo, R.P., Bartholomew, M.J., Hibbard, J.P., and Karabinos, P.M., eds., From Rodinia to Pangea: The Lithotectonic Record of the Appalachian Region: Geological Society of America Memoir 206, p. 283-306. Volkert, R.A., and Puffer. J.H., 1995, Late Proterozoic diabase dikes of the New Jersey Highlands – A remnant of Iapetan rifting in the north-central Appalachians: U.S. Geological Survey Professional Paper 1565-A, 22 p. Volkert, R.A., Zartman, R.E., and Moore, P.B., 2005, U-Pb zircon geochronology of Meso- proterozoic postorogenic rocks and implications for post-Ottawan magmatism and metallogenesis, New Jersey Highlands and contiguous areas, USA: Precambrian Research, v. 139, p. 1-19. Weller, Stuart, 1903, The Paleozoic faunas: New Jersey Geological Survey, Report on Pa- leontology, v. 3, 462 p. Wherry, E.T., 1909, The early Paleozoic of the Lehigh Valley district, Pennsylvania: Science, new series, v. 30, 416 p. White, I.C., 1882, The geology of Pike and Monroe Counties: Pennsylvania Geological Sur- vey, 2nd series, Report G-6, 407 p. Willard, Bradford, 1937, Hamilton correlation: American Journal of Science, v. 33, p. 264- 278. Wolff, J.E., and Brooks, A.H., 1898, The age of the Franklin white limestone of Sussex County, New Jersey: U.S. Geological Survey 18th Annual Report, pt. 2, p. 425- 457. Zartman, R.E., Brock, M.R., Heyl, A.V., and Thomas, H.H., 1967, K-Ar and Rb-Sr ages of some alkalic intrusive rocks from the central and eastern United States: American Journal of Science, v. 265, p. 848-870.

APPROXIMATE MEAN DECLINATION, 2005 by … is spatially associated with marble or amphibolite. 79 Ybh _ thite, oligoclase, and biotite. Commonly contains garnet, magnetite, and trace

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Page 1: APPROXIMATE MEAN DECLINATION, 2005 by … is spatially associated with marble or amphibolite. 79 Ybh _ thite, oligoclase, and biotite. Commonly contains garnet, magnetite, and trace

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Yb

YmpYlo

Yp

Ylh

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Ylo

Ylo

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Sg

Sg

Sg

74o37’30’’41o07’30’’

(BRANCHVILLE)

41o07’30’’74o30’

(WAWAYANDA)

41o00’74o30’

(BOONTON)

41o00’74o37’30”

(STA

NHOPE)35’ 32’30”(DOVER)

(HAMBURG)

5’5’

35’ 32’30”

(NE

WTO

N E

AS

T)

(NE

WFO

UN

DLA

ND

)

2’30’’2’30’’

A

A’

B

B’

1,000

SEA LEVEL

-1,000

-2,000

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2,000

1,000

SEA LEVEL

-1,000

-2,000

FEET

2,000

B B’

Wal

lkill

Riv

er

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rta T

hrus

t Fau

lt

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t Fau

lt

Res

ervo

ir Fa

ult

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sia

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t

Bow

ling

Gre

en M

ount

ain

Long

woo

d Va

lley

Faul

t

Long

woo

d Va

lley

Gor

ge F

ault

YbhYbh

YbYb

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YpgYpg

Ypg

Ypg

Yp

Yp

Yp

Yp

YloYlo

Ylo

Ylo

Ym

Ym

Yk

Ybs

Ybs

_a

_l

_hYu

Yu

Ymh

Yps

Ypg

Yps

Yps

Yps

Yps

Yb

Ylb

Yba

Dcw

Dkec

Dkec

DkecDbv

Dcw

Sbp

Sbp

SbpSg

SgSg Sl

Sl

Sl

Ym

Yps Ymh

Ybh

Ybh

Ymh

_h

1,000

SEA LEVEL

-1,000

-2,000

FEET

2,000

A

1,000

SEA LEVEL

-1,000

-2,000

FEET

2,000

A’

Ham

burg

Fau

lt

Tran

quili

ty T

hrus

t Fau

lt

Zero

Fau

lt

Eas

t Fau

lt

_l

_a

_a

_l

_h

_h

YloYa

Ylb

Ym

Ylo

YaYlb

_a_h

_l

Ylo Ym Ylb

Ym

Ylb

YfwYlb

Ylo

Ylo

YgpYgp Yp

Yp

Ygp

Yu

YmYlb

Ygp

Ylh

Yff_a

_a

_h

_l

Yu

Yff Ybh Ybs

Ybh

Ylo Ybs

Yk Ylb

Ypg

Ype

Ype

Ymp

Yh

Ym

Ylo

YloYb

YbYlh

Ylh

Yp Ypg

Ybh

Yb

Ylo

CORRELATION OF MAP UNITSGREEN POND MOUNTAIN REGION

Unconformity

Unconformity

Unconformity

Unconformity

NEW JERSEY HIGHLANDS

Intrusive ContactsVernon Supersuite

Byram Intrusive Suite Lake Hopatcong Intrusive Suite

Back Arc Supracrustal RocksIntrusive Contacts

Magmatic Arc RocksLosee Metamorphic Suite

Other Rocks

KITTATINNY VALLEY SEQUENCE

Intrusive Contacts

Intrusive Contacts

KittatinnySupergroup

VALLEY AND RIDGEBeemerville Intrusive Suite

Dbv

Dcw

Dkec

Sbp

Sl

Sg

_a

_l

_h

Ya

Ylh

Yma

YhYlbYlo

Yk Ym Yb Ymh Ymp Yp Ype Yff/Yfw

Ybh Ybs Ypg Ypa Yps

Ygp

Zch

Zd

SOl

Yu

DEVONIAN

SILURIAN

SILURIAN andORDOVICIAN

CAMBRIAN

NEOPROTEROZOIC

MESOPROTEROZOIC

N

%5101520

5

10

15

20

Avg trend = N46oESector angle = 10o

n = 67

Figure 1. Rose diagram of bedding strikes in Lower Paleozoic rocks of the Kittatinny Valley sequence.

N

%105 15 20

10

15

20

Avg trend = N66oWSector angle = 10o

n = 28

Figure 3. Rose diagram of joint strikes in Lower Paleozoic rocks of the Kittatinny Valley sequence.

N

%10

10

20

30

20 30

Avg trend = N59oWSector angle = 10o

n = 957

Figure 4. Rose diagram of joint strikes in Mesoproterozoic rocks.

N

%1020

10

20

Avg trend = N34oESector angle = 10o

n = 943

Figure 2. Rose diagram of crystallization foliation strikes inMesoproterozoic rocks.

Bedrock geology mapped by R.A. Volkert and D.H Monteverdein 1987, 2005 and 2012.

Middle Paleozoic geology adapted from S.G. Barnett III (1976)and G.C. Herman and J.P. Mitchell (1991).

Digital cartography by R.S. Pristas and N.L. Malerba.Reviewed by E. Verbeek and M. Gorring.

Research supported by the U. S. Geological Survey, National Cooperative Geologic Mapping Program,

under USGS award number 05HQAG0026. The views and conclusions contained in this document

are those of the author and should not be interpreted as necessarily representing the official policies,

either expressed or implied, of the U. S. Government.

Mapped by the Army Map Service.Edited and published by the United States Geological Survey, 1954

Control by USGS, USC&GS, and New Jersey Geodetic Survey

Topography form aerial photographs by stereophotogrammetric meth-ods. Aerial photographs taken 1942. Culture revised by the United States Geological Survey 1954.

Polyconic projection. 1927 North American datum 10,000-foot grid based on New Jersey coordinate system 1000-meter Universal Transverse Mercator grid ticks, zone 18.

Bedrock Geologic Map of the Franklin Quadrangle Sussex and Morris Counties, New Jersey

byRichard A. Volkert and Donald H. Monteverde

2013

LOCATION IN NEW JERSEY

7000 FEET000 0000 2000 3000 4000 5000 6000

.5 1 KILOMETE R1 0

SCALE 1:24 00021 0 1 MILE

1

,

1

.5

CONTOUR INTERVAL 20 FEET

DEPARTMENT OF ENVIRONMENTAL PROTECTIONWATER RESOURCES MANAGEMENTNEW JERSEY GEOLOGICAL AND WATER SURVEY

Prepared in cooperation with theU.S. GEOLOGICAL SURVEY

NATIONAL GEOLOGIC MAPPING PROGRAM

BEDROCK GEOLOGIC MAP OF THE FRANKLIN QUADRANGLESUSSEX AND MORRIS COUNTIES, NEW JERSEY

GEOLOGIC MAP SERIES GMS 13-3

62

40

Fe

65

18

33

UD

R

R

UD

Contact - Dotted where concealed

Fault - Dotted where concealed. Queried where uncertain. Arrow shows dip direction and attitude of fault, where known.

Normal fault - U, upthrown side; D, downthrown side

Reverse fault - U, upthrown side; D, downthrown side

Strike slip - Arrows indicate relative horizontal movement

Inclined thrust fault - teeth on upper plate

Brittle deformation zone

FOLDS

Folds in Proterozoic rocks showing trace of axial surface, direction and dip of limbs, and direction of plunge.

Overturned antiform

Overturned synform

Antiform

Synform

Folds in Paleozoic rocks showing trace of axial surface, direction and dip of limbs, and direction of plunge. Folds in bedding and/or cleavage.

Anticline

Syncline

PLANAR FEATURES

Strike and dip of beds

Inclined

Vertical

Overturned

Strike and dip of crystallization foliation

Inclined

Vertical

Strike and dip of mylonitic foliation

LINEAR FEATURES

Bearing and plunge of mineral lineation in Proterozoic rocks

OTHER FEATURES

Abandoned mine - Fe, magnetite; Zn, zinc; G, graphite

Abandoned rock quarry

Active rock quarry

Bedrock float used to construct map

Form line showing foliation in Mesoroterozoic rocks. Shown in cross section only.

EXPLANATION OF MAP SYMBOLS

MA

GN

ETIC N

ORTH

APPROXIMATE MEANDECLINATION, 2005

TRUE N

ORTH

13°

INTRODUCTIONThe Franklin quadrangle is located in southeastern Sussex County, northwestern Mor-

ris County, and western Passaic County, where it straddles the boundary between the New Jersey Highlands and Valley and Ridge physiographic provinces, but it is predominantly in the Highlands. The area is characterized by rugged uplands with ridge top elevations of as much as 1,410 ft. above sea level, separated by broad, generally northeast-striking stream valleys. The valleys are drained by the Wallkill River in the west, the Pequannock River in the northeast, and the Rockaway River in the southeast.

Previous work on the bedrock geology of the quadrangle includes that of Spencer and others (1908), Hague and others (1956), Baker and Buddington (1970), and Drake and others (1996). The bedrock lithologies and structures depicted on these maps lacks confor-mity with more recent detailed mapping of adjacent areas. Moreover, new interpretations of bedrock geologic relationships, based in part on detailed bedrock mapping, major and trace element geochemistry, stable isotope analysis, and uranium-lead (U-Pb) geochronology, have updated much of the previous work.

STRATIGRAPHYPaleozoic rocks

Paleozoic rocks in the map area range in age from Cambrian through Devonian and are subdivided into the Middle Paleozoic rocks of the Green Pond Mountain Region and Lower Paleozoic rocks of the Kittatinny Valley sequence. Middle Paleozoic rocks crop out in the Green Pond Mountain Region, a northeast-trending block of downfaulted and folded sedi-mentary rock in the southeast part of the area. They include the Green Pond Conglomerate, Longwood Shale, Poxino Island, and Berkshire Valley Formations of Silurian age, and the Connelly Conglomerate, Esopus Formation, Kanouse Sandstone, Cornwall Shale, and Bell-vale Sandstone of Devonian age. The stratigraphic relationships of the Middle Paleozoic rocks were discussed by Darton (1894), Kümmel and Weller (1902), Barnett (1970), and Herman and Mitchell (1991).

Formations of Cambrian through Ordovician age of the Kittatinny Valley sequence crop out in the lowland areas of the Wallkill Valley, Wildcat Brook, and Big Springs, where they unconformably overlie, or are in fault contact with, Mesoproterozoic rocks. The Kittatinny Valley sequence was previously considered part of the Lehigh Valley sequence of MacLachlan (1979) but was reassigned by Drake and others (1996). It includes the Kittatinny Supergroup, of which the Leithsville Formation and Allentown Dolomite are exposed in the quadrangle. Based on the final acceptance of the Global Stratotype Section and Point base (GSSP) for the Ordovician at Green Point, Newfoundland (Cooper and others, 2001), the Cambrian-Ordovician boundary in New Jersey is now accepted as occurring within the lower third of the Epler Formation, at the top of the Cordylodus lindstromi zone, within conodont fauna B as used in Karklins and Repetski (1989). Therefore, the Allentown Dolomite is now regarded as Cambrian in age.

North of Franklin Pond, northwest-striking lamprophyre dikes of Lower Silurian to Upper Ordovician age of the Beemerville Intrusive Suite (Drake and Monteverde, 1992) intrude the Franklin Marble of Mesoproterozoic age, and the west limb of the zinc orebody at the Franklin mine. Elsewhere regionally, titanite from nepheline syenite at Beemerville yields a TIMS U-Pb crystallization age of 447 ± 2 Ma (Ratcliffe and others, 2012), a K-Ar cooling age from biotite of 435 ± 20 Ma (Zartman and others, 1967), and a fission-track age from titanite of 422 ± 14 Ma (Eby and others, 1992).

Neoproterozoic rocksMesoproterozoic rocks along the eastern side of the Wallkill Valley, north of Morris Lake,

and along the southwestern part of Bowling Green Mountain, are unconformably overlain by unmetamorphosed rocks of the Neoproterozoic Chestnut Hill Formation (Drake, 1984; Gates and Volkert, 2004). Elsewhere regionally, the Chestnut Hill Formation is unconform-ably overlain by the Lower Cambrian Hardyston Quartzite. Rocks of the Chestnut Hill For-mation were formed from alluvial, fluvial, and lacustrine sediments, and possible volcanic rocks of felsic composition, that were deposited in a series of small sub-basins along the rifted margin of eastern Laurentia at about 600 Ma during breakup of the supercontinent Rodinia (Volkert and others, 2010a).

Mesoproterozoic rocks in the map area, but not the Cambrian or younger Paleozoic rocks, are intruded by east or northeast-striking diabase dikes of Neoproterozoic age (Volk-ert and Puffer, 1995). The dikes are characterized by sharp, mainly discordant contacts against enclosing country rocks, aphanitic chill margins, and they contain xenoliths of Me-soproterozoic rocks. Some dikes have columnar joints along their margins, suggesting that the magma may locally have broken the surface as flows that are now eroded. Dikes have geochemical compositions that are high in TiO2, P2O5, Zr, and light rare-earth elements, indicating they were formed from an Ocean Island Basalt-like mantle source in a rift-relat-ed, within-plate, tectonic setting (Volkert, 2004a). Contacts between diabase dikes and the Chestnut Hill Formation are not known to be exposed in the Highlands, so the temporal relationship between them remains unknown.

Mesoproterozoic rocksMesoproterozoic rocks in the map area consist of an assemblage of granites, gneisses,

and marble. Most Mesoproterozoic rocks were metamorphosed to granulite facies during the Ottawan phase of the Grenville orogenic cycle at 1045 to 1024 Ma (Volkert and others, 2010b). The temperature for this high-grade metamorphism is constrained from regional calcite-graphite geothermometry to 769oC (Peck and others, 2006).

Among the oldest Mesoproterozoic rocks in the area are the Losee Suite that formed in a magmatic arc, and a thick assemblage of supracrustal metavolcanic and metasedi-mentary rocks formed in a back-arc basin inboard of the Losee arc (Volkert, 2004b). Rocks of the Losee Suite are calc-alkaline in composition and include various quartz-plagioclase gneisses and amphibolite formed from plutonic and volcanic protoliths (Volkert and Drake, 1999). Rocks of the Losee Suite yield sensitive high-resolution ion microprobe (SHRIMP) U-Pb zircon ages of 1282 to 1248 Ma (Volkert and others, 2010b).

Spatially and temporally associated with the Losee Suite are supracrustal rocks that include microcline gneiss and amphibolite formed from felsic and mafic volcanic protoliths, respectively, and quartzofeldspathic gneisses, calc-silicate rocks, and marble formed from sedimentary protoliths. Microcline gneiss yields U-Pb SHRIMP zircon ages of 1299 to 1251 Ma (Volkert and others, 2010b) that closely overlap the age of rocks of the Losee Suite.

Granite and related rocks of the Byram and Lake Hopatcong Intrusive Suites, that to-gether comprise the Vernon Supersuite (Volkert and Drake, 1998), are abundantly exposed in the map area where they intrude Losee Suite and supracrustal rocks. Byram and Lake Hopatcong rocks form a complete differentiation series that includes monzonite, quartz monzonite, granite, and alaskite, all of which have a distinctive A-type geochemical compo-sition (Volkert and others, 2000). Granite of both suites yields similar U-Pb SHRIMP zircon ages of 1188 to 1182 Ma (Volkert and others, 2010b).

The youngest Mesoproterozoic rocks are postorogenic potassic granites and granite pegmatites that are undeformed, contain xenoliths of foliated gneiss or marble, and intrude other Mesoproterozoic rocks in the map area as small, tabular to irregular bodies that are discordant to the metamorphic foliation. Pegmatite known locally as Double Rock, that in-trudes marble and the west limb of the zinc orebody at the Franklin mine, has a U-Pb zircon age of 986 Ma, and other regional postorogenic bodies of granite and pegmatite yield U-Pb zircon ages of 1004 to 990 Ma (Volkert and others, 2005).

STRUCTUREPaleozoic bedding and cleavage

Bedding in the Paleozoic rocks is fairly uniform and strikes northeast except in the hinge areas of folds at Bowling Green Mountain. The average strike of bedding in Middle Paleozoic rocks of the Green Pond Mountain Region is N.39oE. Beds range in dip from 22o to 90o and average 60o. Most beds are upright and dip northwest and, less commonly, southeast, although locally in the Longwood Valley they are overturned. The average strike of bedding in Lower Paleozoic rocks of the Kittatinny Valley sequence is N.46oE. (fig. 1). Beds range in dip from 11o to 90o and average 44o. They dip mainly northwest and, less commonly, southeast.

Cleavage (closely spaced parallel partings) is present in most of the Paleozoic rocks but is best developed in shale and other fine-grained rocks. Cleavage in rocks of the Green Pond Mountain Region strikes about N.43oE. and in rocks of the Kittatinny Valley sequence about N.53oE., nearly parallel to the strike of bedding in both the Middle and Lower Pa-leozoic rocks. Cleavage dips mainly southeast at an average of 75o in Middle Paleozoic rocks, and toward the northwest or southeast at an average of 43o in the Lower Paleozoic rocks.

Proterozoic foliationCrystallization foliation, formed by the parallel alignment of mineral grains in the Me-

soproterozoic rocks, defines the trend of the bedrock. It is an inherited feature from com-pressional stresses during granulite-facies metamorphism that deformed the rocks between 1045 and 1024 Ma (Volkert and others, 2010b). Foliation strikes mainly northeast at an average of N.34oE. (fig. 2), but locally, in the hinges of folds, it strikes northwest because of deformation of the rocks during folding. Foliation dips southeast and, less commonly, north-west at 30o to 90o and averages 65o. Northwest-striking foliation dips gently to moderately northeast.

FoldsFolds in the Paleozoic rocks were formed during the Taconian and Alleghanian oroge-

nies at about 450 Ma and 250 Ma, respectively. Folds in the Green Pond Mountain Region are northeast, open to tight, upright to locally overturned, and gently inclined to recumbent anticlines and synclines (Barnett, 1976; Herman and Mitchell, 1991). Most folds plunge gently southwest. Taconic-age folds here are cut by younger Alleghanian faults (Herman and Monteverde, 1989; Herman and others, 1997). Folds in rocks of the Kittatinny Valley sequence are northeast, open, upright, and form gently north-plunging anticlines and syn-clines that continue from Lake Mohawk to the south (Drake and Volkert, 1993).

Folds that deform Mesoproterozoic rocks originated during the Ottawan phase of the Grenville orogeny. They deform earlier-formed planar metamorphic fabrics and, therefore, postdate the development of crystallization foliation. Characteristic fold patterns are broad, open, northwest-verging to locally upright, northeast-plunging antiforms and synforms. Min-eral lineations plunge parallel to the axes of major folds. Plunges range from 13o to 53o and average 31oN.52oE.

FaultsThe structural geology of the bedrock units is dominated by northeast-trending faults

that deform Mesoproterozoic and Paleozoic rocks. Most faults are characterized by brit-tle deformation features that include brecciation, recrystallization and low-temperature retrogression of mafic minerals, chlorite or epidote-coated slickensides, and close-spaced fracture cleavage. The Zero and Reservoir faults are characterized by ductile deformation features that include mylonite, shear band foliation, and boudinage, overprinted by brittle deformation features.

The Tranquility thrust fault strikes northeast and dips gently to moderately southeast at an average of 35o. The fault places Mesoproterozoic and Paleozoic rocks on the hanging wall against Paleozoic dolomite on the footwall. It extends through the northwest corner of the map area, and is also known to the southwest, in the Tranquility quadrangle, where it was encountered in drill core by New Jersey Zinc Company geologists (Baum, 1967), and in the Newton East quadrangle, where the fault was inferred by Drake and Volkert (1993), and later confirmed through drilling in 2009 at the Limecrest quarry (Volkert, 2010). The fault is characterized by early ductile deformation that is strongly overprinted by brittle deformation features.

The Hamburg fault strikes northeast and dips southeast at about 75o. It places Meso-proterozoic rocks on the footwall against Paleozoic rocks on the hanging wall along most of its length. The latest movement appears to have been normal. The fault is characterized by brittle deformation features along its entire length.

The Zero fault strikes northeast and dips steeply southeast to vertically. It bounds the west side of the Wallkill River Valley where it places Mesoproterozoic rocks on the footwall against Paleozoic rocks on the hanging wall. The fault is characterized by ductile deforma-tion features of Proterozoic age that are overprinted by brittle deformation fabric of probable Paleozoic age (Metsger, 2001). The fault has a protracted history of movement through geologic time, but the latest movement sense appears to be normal. The Zero fault termi-nates in a series of splays in the northern part of the map area where it is cut off by the East fault.

The Sparta thrust fault strikes northeast and dips nearly horizontally to about 35o south-east. To the south, in the Newton East quadrangle, it was interpreted as a northwest-dipping back thrust (Drake and Volkert, 1993), but it is here reinterpreted as a folded thrust fault based on movement indicators in Allentown Dolomite near Sparta. The fault is cut off on both ends by the Zero fault. The Sparta thrust fault has Paleozoic rocks along most of its length, but in the map area it extends along the east side of the Wallkill River Valley, where it has Paleozoic rocks on the footwall and Mesoproterozoic rocks on the hanging wall. The fault is characterized by brittle deformation fabric along its entire length.

The East fault strikes northeast and dips southeast about 80o. It borders the east side of the Wallkill River Valley, where it has Mesoproterozoic rocks along most of its length, but in the map area it places Paleozoic rocks on the footwall against Mesoproterozoic rocks on the hanging wall. The latest movement on the fault appears to have been reverse. The fault is characterized by brittle deformation fabric along its entire length.

The Reservoir fault strikes northeast and ranges in dip from steeply northwest to steeply southeast. It places Mesoproterozoic rocks on the footwall against Paleozoic rocks on the hanging wall along most of its length. The fault has undergone multiple reactivations dating from the Proterozoic that indicate normal, right-lateral strike slip, and reverse movement, with latest movement having been normal. The fault is characterized by ductile deformation features in the center of the fault zone that are overprinted by a zone of brittle deformation as much as 1,000 feet wide.

The Russia fault (Herman and Mitchell, 1991) strikes N.50oE., closely paralleling the adjacent Reservoir fault, and dips southeast at about 80o. It is bounded by Paleozoic rocks on both sides. South of the map area the fate of the fault is unknown, and to the north, in the Newfoundland quadrangle, it merges with, or is cut off by, the Reservoir fault. Latest movement on the fault appears to have been normal. The fault is characterized by brittle deformation fabric.

The Longwood Valley fault strikes about N.45oE. and dips steeply northwest to verti-cally. It has Mesoproterozoic rocks on the footwall and Paleozoic rocks on the hanging wall along most of its length. Kinematic indicators suggest the latest movement on the fault was reverse, although dip-slip normal movement is predominant south of the map area. The fault is characterized by brittle deformation fabric.

Mesoproterozoic and Paleozoic rocks are also deformed by small faults striking north-east or northwest that range from a few inches to tens of feet wide and are rarely more than a few thousand feet long. These faults are characterized mainly by brittle deformation features. Latest movement is varied and ranges from normal, to right-lateral or left-lateral strike slip.

JointsJoints are a ubiquitous feature in the Mesoproterozoic and Paleozoic rocks but are best

developed in massive rocks such as Paleozoic limestone, dolomite, and sandstone, and in Mesoproterozoic granite and some gneiss. Joints developed in Mesoproterozoic rocks are characteristically planar, moderately well formed, moderately to widely spaced, and moder-ately to steeply dipping. Their surfaces are typically unmineralized, except near faults, and are smooth and less commonly slightly irregular. Joints are varied in their spacing from a foot to tens of feet apart. Those formed close to faults are spaced 2 feet or less apart.

The dominant joints in the Green Pond Mountain Region strike N.49oW. on average and dip mainly northeast at an average of 76o. Joints in rocks of the Kittatinny Valley sequence strike N.66oW. on average (fig. 3) and dip southwest at an average of 76o. A minor set strikes N.35oE. and dips nearly equally southeast or northwest at an average of 53o.

The dominant joints in the Mesoproterozoic rocks are nearly perpendicular to the strike of crystallization foliation, a consistent feature in Mesoproterozoic rocks throughout the Highlands (Volkert, 1996). Therefore, the strike of joints is somewhat varied because of folding. The dominant joints strike N.59oW. (fig. 4) and dip moderately to steeply southwest at an average of 76o.

ECONOMIC RESOURCES Mesoproterozoic rocks in the quadrangle host economic deposits of iron ore (magne-

tite), zinc ore (franklinite, zincite, and willemite), and graphite that were mined predominant-ly during the 19th century. Magnetite was extracted from mines hosted by Mesoproterozoic granite, gneiss, and, very locally, marble. Detailed descriptions of most of the mines are given in Bayley (1910) and Baker and Buddington (1970). Marble-hosted zinc-iron-manga-nese ore was mined at the world-famous Franklin mine (Frondel and Baum 1974) and Ster-ling Hill mine (Metsger and others, 1958, Metsger, 2001, Johnson, 2001) in the northwest part of the map area. Both zinc deposits have been the subject of geologic inquiry for more than a century, and a complete bibliography of references pertaining to these deposits is given in Dunn (1995). Graphite was mined during the 19th century from rusty-weathering biotite-quartz-feldspar gneiss at a single location west of Oak Ridge Reservoir.

Mesoproterozoic marble in the northwest part of the map was quarried for crushed stone at several locations, and is currently quarried at a single location north of the Sterling Hill mine.

The Neoproterozoic Chestnut Hill Formation hosts a deposit of hematite that was mined during the 19th century on the east side of the Wallkill River Valley. The deposit was small, and no record of mining is known, so this may not have been a producing mine.

DESCRIPTION OF MAP UNITS Green Pond Mountain RegionBellvale Sandstone (Middle Devonian) (Bellvale Flags of Darton, 1894; Willard, 1937) -

Upper beds are grayish-red to grayish-purple sandstone containing quartz pebbles as large as 1 in. in diameter. Lower beds are light-olive-gray to yellowish-gray- and green-ish-black-weathering, medium-gray to medium-bluish-gray, very thin to very thick-bed-ded siltstone and sandstone, crossbedded, graded, and interbedded with black to dark-gray shale. More sandstone occurs in upper beds and is finer downward. Lower contact conformable with the Cornwall Shale and placed where beds are thicker and volume of shale and siltstone is about equal. Unit is 1,750 to 2,000 ft. thick.

Cornwall Shale (Middle Devonian) (Hartnagel, 1907) – Black to dark-gray, very thin to thick-bedded, fossiliferous shale, interbedded with medium-gray and light-olive-gray to yellowish-gray, laminated to very thin bedded siltstone that is more abundant in upper part. Lower contact with Kanouse Sandstone probably conformable. Unit is about 950 ft. thick.

Kanouse Sandstone, Esopus Formation, and Connelly Conglomerate, undivided (Lower Devonian) Kanouse Sandstone (Kümmel, 1908) – Medium-gray, light-brown, and grayish-red, fine to coarse-grained, thin to thick-bedded sandstone and pebble con-glomerate. Basal conglomerate is interbedded with siltstone and contains well-sorted, subangular to subrounded, gray and white quartz pebbles less than 0.4 in. long. Lower contact with Esopus Formation gradational. Unit is about 46 ft. thick.

Esopus Formation (Vanuxem, 1842; Boucot, 1959) – Light to dark-gray, laminated to thin-bedded siltstone interbedded with dark-gray to black mudstone, dusky-blue sand-stone and siltstone, and yellowish-gray, fossiliferous siltstone and sandstone. Lower contact probably conformable with Connelly Conglomerate. Unit is about 180 ft. thick in the map area.

Connelly Conglomerate (Chadwick, 1908) – Grayish-orange-weathering, very light-gray to yellowish-gray, thin-bedded quartz-pebble conglomerate. Quartz pebbles are subround-ed to well rounded, well sorted, and as much as 0.8 in. long. Unit is about 36 ft. thick.

Berkshire Valley and Poxono Island Formations, undivided (Upper Silurian) Berkshire Valley Formation (Barnett, 1970) – Yellowish-gray-weathering, medium-gray to pink-ish-gray, very thin to thin-bedded fossiliferous limestone interbedded with gray to green-ish-gray calcareous siltstone and silty dolomite, medium-gray to light-gray dolomite conglomerate, and grayish-black thinly laminated shale. Lower contact conformable with Poxino Island Formation. Unit ranges in thickness from 90 to 125 ft.

Poxono Island Formation (White, 1882; Barnett, 1970) – Very thin to medium-bedded se-quence of medium-gray, greenish-gray, or yellowish-gray, mud-cracked dolomite; light-green, pitted, medium-grained calcareous sandstone, siltstone, and edgewise conglom-erate containing gray dolomite; and quartz-pebble conglomerate containing angular to subangular pebbles as much as 0.8 in. long. Interbedded grayish-green shale at lower contact is transitional into underlying Longwood Shale. Unit ranges in thickness from 160 to 275 ft.

Longwood Shale (Upper to Middle Silurian) (Darton, 1894) – Dark reddish-brown, thin to very thick-bedded shale interbedded with cross-bedded, very dark-red, very thin- to thin-bedded sandstone and siltstone. Lower contact conformable with Green Pond Conglomerate. Unit is about 330 ft. thick.

Green Pond Conglomerate (Middle to Lower Silurian) (Rogers, 1836) - Medium to coarse-

grained quartz-pebble conglomerate, quartzitic arkose and orthoquartzite, and thin to thick-bedded reddish-brown siltstone. Grades downward into less abundant gray, very dark red, or grayish-purple, medium to coarse-grained, thin- to very thick-bedded peb-ble to cobble-conglomerate containing clasts of red shale, siltstone, sandstone, and chert; yellowish-gray sandstone and chert; dark-gray shale and chert; and white-gray and pink milky quartz. Quartz cobbles are as much as 4 in. long. Unconformably over-lies, or is in fault contact with, Mesoproterozoic rocks. Unit is about 1,000 ft. thick.

Valley and Ridge Beemerville Intrusive SuiteLamprophyre dikes (Lower Silurian to Upper Ordovician) – Light-medium- to medi-

um-dark-gray, fine-grained to aphanitic dike of mainly alkalic composition. Contacts are chilled and sharp against enclosing Mesoproterozoic country rock. Dike is exposed in the Buckwheat open cut at the Franklin zinc mine, north of Franklin Pond. It is as much as 25 ft. wide and of uncertain length.

Kittatinny Valley SequenceAllentown Dolomite (Upper Cambrian) (Wherry, 1909) – Upper sequence is light-gray- to

medium-gray-weathering, medium-light- to medium-dark-gray, fine to medium-grained, locally coarse-grained, medium to very thick-bedded dolomite; local shaly dolomite near the bottom. Floating quartz sand and two series of medium-light- to very light-gray, medium-grained, thin-bedded quartzite and discontinuous dark-gray chert lenses occur directly below upper contact. Lower sequence is medium- to very-light-gray-weathering, light- to medium dark-gray, fine to medium-grained, thin to medium-bedded dolomite and shaly dolomite. Weathered exposures characterized by alternating light and dark-gray beds. Ripple marks, ooids, algal stromatolites, cross-beds, edgewise conglomer-ate, mud cracks, and paleosol zones occur throughout but are more abundant in lower sequence. Lower contact gradational into Leithsville Formation. Unit contains a trilobite fauna of Dresbachian (early Late Cambrian) age (Weller, 1903; Howell, 1945). Unit is about 1,800 ft. thick regionally.

Leithsville Formation (Middle to Lower Cambrian) (Wherry, 1909) – Upper sequence, rarely exposed, is mottled, medium-light- to medium-dark-gray-weathering, medium- to medium-dark-gray, fine to medium-grained, medium to thick-bedded, locally pitted and friable dolomite. Middle sequence is grayish-orange or light- to dark-gray, gray-ish-red, light-greenish-gray- or dark-greenish-gray-weathering, fine-grained, thin to medium-bedded dolomite, argillaceous dolomite, dolomitic shale, quartz sandstone, siltstone, and shale. Lower sequence is medium-light- to medium-gray-weathering, medium-gray, fine to medium-grained, thin- to medium-bedded dolomite. Quartz-sand lenses occur near lower gradational contact with Hardyston Quartzite. Archaeocyathids of Early Cambrian age are present in formation at Franklin, New Jersey, suggesting an intraformational disconformity between Middle and Early Cambrian time (Palmer and Rozanov, 1967). Unit also contains Hyolithellus micans (Offield, 1967; Markewicz, 1968). Thickness is approximately 800 ft. regionally.

Hardyston Quartzite (Lower Cambrian) (Wolff and Brooks, 1898) – Medium to light-gray, fine to coarse-grained, medium to thick-bedded pebble conglomerate, quartzite, arkosic sandstone and dolomitic sandstone. Conglomerate contains subangular to subrounded white quartz pebbles as much as 1 in. long. Lower contact unconformable with Meso-proterozoic rocks. Contains Scolithus linearis (?) and fragments of the trilobite Olenellus thompsoni of Early Cambrian age (Nason, 1891; Weller, 1903). Thickness regionally is as much as 30 ft.

New Jersey HighlandsDiabase dikes (Neoproterozoic) (Volkert and Puffer, 1995) – Light-gray or brown-

ish-gray-weathering, dark-greenish-gray, aphanitic to fine-grained dikes. Composed principally of plagioclase (labradorite to andesine), augite, and iron-titanium oxides. Py-rite blebs are common. Contacts are chilled and sharp against enclosing Mesoprotero-zoic rocks. Dikes are as much as 40 feet wide and 0.5 mile or more long.

Chestnut Hill Formation (Neoproterozoic) (Drake, 1984; Gates and Volkert, 2004) – In-terbedded sequence of gray, brownish-gray, greenish-gray, tan, or light green, medi-um-grained, thin-bedded lithic sandstone, quartzose sandstone, siltstone, pebble con-glomerate, and thin ironstone beds. Conglomerate contains subangular to subrounded clasts of quartz and feldspar. Interbedded coarser-grained lithologies locally are as much as 6 ft. thick, but are not laterally continuous and likely are channel deposits. Graded beds, tabular cross beds, rip-up clasts, slump folds, load casts, and clastic dikes are common. Thickness regionally is as much as 40 ft.

Granite pegmatite (Mesoproterozoic) – Pinkish-gray or buff-weathering, pinkish-white or light-pinkish-gray, coarse- to very-coarse-grained, massive, unfoliated granite. Com-posed of microcline microperthite, quartz, oligoclase, and local hornblende. Intrudes most other Mesoproterozoic rocks in the map area as tabular to irregular bodies of varied thickness that are discordant to crystallization foliation.

Vernon Supersuite (Volkert and Drake, 1998) Byram Intrusive Suite (Drake and others, 1991)Hornblende granite (Mesoproterozoic) – Pinkish-gray or buff-weathering, pinkish-white

or light-pinkish-gray, medium- to coarse-grained, massive, foliated granite composed principally of microcline microperthite, quartz, oligoclase, hornblende, and local zircon, apatite, and magnetite. Unit grades into alaskite with decrease in concentration of horn-blende and into monzonite with decrease in quartz. Includes bodies of pegmatite and amphibolite too small to show on the map.

Hornblende monzonite (Mesoproterozoic) – Pinkish-gray or buff-weathering, pinkish-gray or greenish-gray, medium to coarse-grained, massive, foliated monzonite, and less abundant syenite or quartz monzonite, composed of microcline microperthite, oligo-clase, hornblende, and quartz. Contains sparse amounts of pyroxene where in contact with rocks of the Lake Hopatcong Intrusive Suite.

Lake Hopatcong Intrusive Suite (Drake and Volkert, 1991)Pyroxene granite (Mesoproterozoic) – Buff or white-weathering, greenish-gray, medium to

coarse-grained, massive, foliated granite composed of mesoperthite to microantiper-thite, quartz, oligoclase, and clinopyroxene. Locally contains titanite, magnetite, apatite, and trace amounts of zircon and pyrite. Unit grades into alaskite with decrease in con-centration of clinopyroxene and into monzonite with decrease in quartz.

Pyroxene alaskite (Mesoproterozoic) – Buff or white-weathering, greenish-buff or light- pinkish-gray, medium to coarse-grained, massive, moderately foliated granite com-posed of mesoperthite to microantiperthite, quartz, oligoclase, and sparse amounts of clinopyroxene. Commonly contains titanite, magnetite, apatite, and trace amounts of zircon.

Pyroxene monzonite (Mesoproterozoic) – Gray, buff, or tan-weathering, greenish-gray, medium to coarse-grained, massive, moderately foliated monzonite to syenite. Com-posed of mesoperthite, microantiperthite to microcline microperthite, oligoclase, clino-pyroxene, titanite, magnetite, and sparse amounts of apatite and quartz.

Back-Arc Basin Supracrustal RocksPotassic feldspar gneiss (Mesoproterozoic) – Light-gray or pinkish-buff-weathering, pink-

ish-white or light-pinkish-gray, medium-grained, moderately foliated gneiss composed of quartz, microcline microperthite, oligoclase, biotite, and magnetite. Garnet, tourma-line, and sillimanite occur locally.

Microcline gneiss (Mesoproterozoic) – Pale pinkish-white-weathering, tan or pinkish-white, medium-grained, layered and foliated gneiss composed of quartz, microcline microper-thite, oligoclase, and biotite. Commonly contains garnet, magnetite, and trace amounts of sillimanite and tourmaline. Unit is spatially associated with marble or amphibolite.

Biotite-quartz-feldspar gneiss (Mesoproterozoic) – Gray-weathering, locally rusty, gray, tan, or greenish-gray, medium to coarse-grained, moderately layered and foliated gneiss containing microcline microperthite, oligoclase, quartz, and biotite. Locally con-tains garnet, sillimanite, and magnetite; graphite and pyrrhotite are confined to the vari-ant that weathers rusty. Unit is spatially associated with amphibolite or pyroxene gneiss.

Hornblende-quartz-feldspar gneiss (Mesoproterozoic) – Light-gray or pinkish-buff-weath-ering, pinkish-white or pinkish-gray, medium-grained, foliated gneiss composed of quartz, microcline microperthite, oligoclase, and hornblende. Locally contains biotite, garnet, and magnetite.

Clinopyroxene-quartz-feldspar gneiss (Mesoproterozoic) – Pinkish-gray or pinkish-buff- weathering, white, pale-pinkish-white, or light-gray, medium to coarse-grained, mod-erately foliated gneiss composed of quartz, microcline, oligoclase, clinopyroxene, and trace amounts of epidote, biotite, titanite, and magnetite.

Pyroxene gneiss (Mesoproterozoic) – White or tan-weathering, greenish-gray, medi-um-grained, layered and foliated gneiss composed of oligoclase, clinopyroxene, and titanite. Contains varied amounts of quartz, magnetite, scapolite, or calcite. Commonly interlayered with amphibolite or marble. Elsewhere, unit contains clots and layers of dark green, medium to coarse-grained rock mapped as diopsidite composed almost entirely of diopside to hedenbergite.

Pyroxene-epidote gneiss (Mesoproterozoic) – Light-greenish-gray or greenish-pink- weathering, pale-pinkish-white or light-greenish-gray, medium-grained, layered and foli-ated gneiss containing quartz, oligoclase, pyroxene, epidote, microcline, scapolite, and titanite. Locally grades into pyroxene gneiss with decrease in epidote and microcline.

Franklin Marble (Mesoproterozoic) – White, pink, or light-gray-weathering, white, light gray, orange, or pink, medium to coarse-grained, calcitic to locally dolomitic marble com-posed mainly of calcite, graphite, and phlogopite. Contains varied amounts of amphi-bole, clinopyroxene and other minerals. Separated by Hague and others (1956) into a lower Franklin marble layer (Yff) and an upper Wildcat marble layer (Yfw) that are separated by gneiss. Locally contains relict karst features that include bedrock pinna-cles, solution caves, and paleo-solution breccia. Franklin marble layer is host rock for zinc-iron-manganese deposits at the Franklin and Sterling Hill mines.

Magmatic Arc Rocks Losee Metamorphic Suite (Drake, 1984; Volkert and Drake, 1999)Quartz-oligoclase gneiss (Mesoproterozoic) – White-weathering, light-greenish-gray, me-

dium to coarse-grained, layered to massive, foliated gneiss composed of oligoclase or andesine, quartz, and varied amounts of hornblende, biotite, clinopyroxene, and mag-netite. Locally contains layers of amphibolite too thin to be shown on the map. Unit commonly has gradational contacts with biotite-quartz-oligoclase gneiss and hyperst-hene-quartz-plagioclase gneiss.

Biotite-quartz-oligoclase gneiss (Mesoproterozoic) – Light-gray-weathering, gray or greenish-gray, medium to coarse-grained, layered and foliated gneiss composed of oligoclase or andesine, quartz, biotite, and trace amounts of garnet. Some outcrops contain hornblende. Unit locally contains thin, conformable layers of amphibolite.

Hornblende-quartz-oligoclase gneiss (Mesoproterozoic) – White or light-gray-weather-ing, greenish-gray, medium to coarse-grained, foliated gneiss composed of oligoclase or andesine, quartz, hornblende, magnetite, and local clinopyroxene.

Hypersthene-quartz-plagioclase gneiss (Mesoproterozoic) – Gray or tan-weathering, greenish-gray or greenish-brown, medium-grained, foliated gneiss composed of andes-ine or oligoclase, quartz, clinopyroxene, hornblende, and hypersthene. Commonly con-tains thin, conformable layers of amphibolite and quartz-plagioclase gneiss containing hornblende and clinopyroxene.

Other rocksAmphibolite (Mesoproterozoic) – Grayish-black-weathering, black or grayish-black, me-

dium-grained, foliated rock composed of hornblende, andesine, and magnetite. Some variants contain biotite and others contain clinopyroxene. Amphibolite associated with the Losee Suite is metavolcanic in origin, and that associated with supracrustal rocks may be metavolcanic or metasedimentary in origin. All types are shown undifferentiated on the map.

Microantiperthite alaskite (Mesoproterozoic) – Tan or buff-weathering, light-greenish-gray, medium to coarse-grained, massive, indistinctly foliated rock composed of micro-antiperthite, brown rust-stained quartz, and oligoclase. Locally contains biotite, horn-blende, altered clinopyroxene, hypersthene, and magnetite. Confined to one small body south of Edison Pond.

Mesoproterozoic rocks, undifferentiated – Shown in cross section only.

Sbp

Sl

Sg

SOl

_a

Ybh

Ybs

Ypg

Ypa

Yps

Yk

Ym

Yb

Ymh

Ymp

Yp

Ype

Yff/Yfw

Ylo

Ylb

Ylh

Yh

Ya

Yma

Yu

_l

_h

Zd

Zch

Ygp

Dbv

Dcw

Dkec

REFERENCES CITED AND USED IN CONSTRUCTION OF MAPBaker, D.R., and Buddington, A.F., 1970, Geology and magnetite deposits of the Franklin

quadrangle and part of the Hamburg quadrangle, New Jersey: U.S. Geological Survey Professional Paper 638, 73 p.

Barnett, S.G., III, 1970, Upper Cayugan and Helderbergian stratigraphy of southeastern New York and northern New Jersey: Geological Society of America Bulletin, v. 81, p. 2375-2402.

________, 1976, Geology of the Paleozoic rocks of the Green Pond outlier: New Jersey Geological Survey Geologic Report Series No. 11, 9 p.

Baum, J.L., 1967, The Tranquility prospect, Sussex County, New Jersey: New Jersey Zinc Company, unpublished interoffice correspondence. On file in the office of the New Jersey Geological Survey, Trenton, New Jersey.

Bayley, W.S., 1910, Iron mines and mining in New Jersey: New Jersey Geological Survey Final Report Series, v. 7, 512 p.

Boucot, A.J., 1959, Brachiopods of the Lower Devonian rocks at Highland Mills, New York: Journal of Paleontology, v. 33, p. 727-769.

Chadwick, H.G., 1908, Revision of “the New York series”: Science, new series, v. 28, p. 346-348.

Cooper, R.A., Nowlan, G.S., and Williams, S.H., 2001, Global Stratotype Section and Point for base of the Ordovician System: Episodes, v. 24, no. 1, p. 19-28.

Darton, N.H., 1894, Geologic relations from Green Pond, New Jersey, to Skunnemunk Mountain, New York: Geological Society of America Bulletin, v. 5, p. 367-394.

Drake, A.A., Jr., 1984, The Reading Prong of New Jersey and eastern Pennsylvania - An appraisal of rock relations and chemistry of a major Proterozoic terrane in the Appalachians, in Bartholomew, M.J., ed., The Grenville event in the Appalachians and related topics: Geological Society of America Special Paper 194, p. 75-109.

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